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THE HAWAIIAN-EMPEROR VOLCANIC CHAIN Part I Geologic Evolution

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THE HAWAIIAN-EMPEROR VOLCANIC CHAIN Part I Geologic Evolution VOLCANISM IN HAWAII Chapter 1 - .-............,. THE HAWAIIAN-EMPEROR VOLCANIC CHAIN Part I Geologic Evolution By David A. Clague and G. Brent Dalrymple ABSTRACT chain, the near-fixity of the hot spot, the chemistry and timing of The Hawaiian-Emperor volcanic chain stretches nearly the eruptions from individual volcanoes, and the detailed geom­ 6,000 km across the North Pacific Ocean and consists of at least etry of volcanism. None of the geophysical hypotheses pro­ t 07 individual volcanoes with a total volume of about 1 million posed to date are fully satisfactory. However, the existence of km3• The chain is age progressive with still-active volcanoes at the Hawaiian ewell suggests that hot spots are indeed hot. In the southeast end and 80-75-Ma volcanoes at the northwest addition, both geophysical and geochemical hypotheses suggest end. The bend between the Hawaiian and .Emperor Chains that primitive undegassed mantle material ascends beneath reflects a major change in Pacific plate motion at 43.1 ± 1.4 Ma Hawaii. Petrologic models suggest that this primitive material and probably was caused by collision of the Indian subcontinent reacts with the ocean lithosphere to produce the compositional into Eurasia and the resulting reorganization of oceanic spread­ range of Hawaiian lava. ing centers and initiation of subduction zones in the western Pacific. The volcanoes of the chain were erupted onto the floor of the Pacific Ocean without regard for the age or preexisting INTRODUCTION structure of the ocean crust. Hawaiian volcanoes erupt lava of distinct chemical com­ The Hawaiian Islands; the seamounts, hanks, and islands of positions during four major stages in their evolution and the Hawaiian Ridge; and the chain of Emperor Seamounts form an growth. The earliest stage is a submarine alkalic preahield array of shield volcanoes that stretches nearly 6,000 km across the stage, which is followed by the tholeiitic shield stage. The shield north Pacific Ocean (fig. 1.1). This unique geologic feature consists stage probably accounts for >95 percent of the volume of each volcano. The shield stage is followed by an alkalic postshield of more than 107 individual volcanoes with a combined volume 3 stage during which a thin cap of alkalic basalt and associated slightly greater than 1 million km (Bargar and Jackson, 1974). The differentiated lava covers the tholeiitic shield. After several chain is age progressive with still-active volcanoes at the southeast million years of erosion, alkalic rejuvenated-stage lava erupts end whereas those at the northwest end have ages of about 75-80 from isolated vents. An individual volcano may become extinct Ma. The volcanic ridge is surrounded by a symmetrical depression, before the sequence is complete. The alkalic preshield stage is only known from recent study of Loihi Seamount. Lava from the Hawaiian Deep, as much as 0.7 km deeper than the adjacent later eruptive stages has been identified from numerous sub­ ocean floor (Hamilton, 1957). The Hawaiian Deep is in turn merged volcanoes located west of the principal Hawaiian surrounded by the broad Hawaiian Arch. Islands. At the southeast end of the chain lie the eight principal Volcanic propagation rates along the chain are 9.2 ± 0.3 em! Hawaiian Islands. Place names for the islands and seamounts in the yr for the Hawaiian Chain and 7.2 ± 1.1 cm/yr for the Emperor Chain. A best fit through all the age data for both chains gives chain are shown in figure 1.1 (see also table 1.2) The Island of 8.6±0.2 em/yr. Alkalic rejuvenated-stage lava erupts on an Hawaii includes the active volcanoes of Mauna Loa, which erupted older shield during the formation of a new large shield volcano in 1984, and Kilauea, which erupted in 1986. Loihi Seamount, 190±30 km to the east. The duration of the quiescent period located about 30 km off the southeast coast of Hawaii, is also active preceding eruption of rejuvenated-stage lava decreases system­ and considered to be an embryonic Hawaiian volcano (Malahoff, atically from 2.5 m.y. on Niihau to <0.4 m.y. at Haleakala, reflecting an increase in the rate of volcanic propagation during chapter 6; Moore and others, 1979, 1982). Hualalai Volcano on the last few million years. Rejuvenated-stage lava is generated Hawaii and Haleakala Volcano on Maui have erupted in historical during the rapid change from subsidence to uplift as the vol­ times. Between Niihau and Kure Island only a few of the volcanoes canoes override a flexural arch created by loading the new rise above the sea as small volcanic islets and coral atolls. Beyond shield volcano on the ocean lithosphere. Kure the volcanoes are entirely submerged beneath the sea. Paleomagnetic data indicate that the Hawaiian hot spot has remained fixed during the last 40 m.y., but prior to that time the Approximately 3,450 km northwest of Kilauea, the Hawaiian hot spot was apparently located at a more northerly latitude. Chain bends sharply to the north and becomes the Emperor The most reliable data suggest about 70 of southward movement Seamounts, which continue northward another 2,300 km. of the hot spot between 65 and 40 Me. It is now clear that this remarkable feature was formed during The numerous hypotheses to explain the mechanism of the the past 70 m.y. or so as the Pacific lithospheric plate moved north hot spot fall into four types: propagating fracture hypotheses, and then west relative to a melting anomaly, called the Hawaiian hot thermal or chemical convection hypotheses, shear melting hypotheses, and heat injection hypotheses. A successful spot, located in the asthenosphere. According to this hot-spot hypothesis must explain the propagation of volcanism along the hypothesis, a trail of volcanoes was formed and left on the ocean 5 u.s. Geological Survey Professional Paper 1350 ... w, , 8 VOLCANISM IN HAWAII 140· 160· 1BO· 120· BERING SEA NORTH AMERICA 400 20' EXPLANATION Age of oceanic crust (Mal .0-40 .106-120 .40-73 0120-150 R73-106 .>150 FIGURE 1.2.-Magnetic anomaliesand structure of ocean floor crust in North Pacific modified from Hilde and others (1976} Hawaiian-Emperor Chain (black) crosscuts preexisting fracture zones and Mesozoic magnetic-anomaly sequence. and small flows of lava richer in SiOz and FeO (these are the the bulk of the shield is built of tholeiitic basalt, but during declinin hawaiite and mugearite that characterize the alkalic postshield activity the magma compositions revert to alkalic basalt. The alkali stage). S. Powers (1920) noted that eruptive centers of nepheline preshield stage, like the alkalic postshield stage, produces only smai basalt on Kauai, Oahu, Molokai, and Maui were active long after volumes of lava, probably totaling less than a few percent of th the main volcano became quiet; he appears to have been the first to volcano. associate nepheline basalt with late-stage eruptions following an We have omitted the main caldera-collapse stage of Stearn erosional hiatus. (1966) from the eruption sequence because it can occur either durin: New insight into the preshield stage has come from recent the shield stage or near the beginning of the alkalic postshield stage studies of Loihi Seamount, a small submarine volcano located about The lava erupted may therefore be tholeiitic or alkalic basalt, or 0 30 km off the southeast coast of Hawaii. Its location, small size, both types. seismic activity, and fresh, glassy lava all indicate that Loihi is an active volcano and the youngest in the Hawaiian-Emperor Chain. GEOLOGY OF THE HAWAIIAN ISLANDS Some of the older lava samples recovered from Loihi Seamount are alkalic basalt and basanite, whereas the youngest lava samples Descriptions of volcanoes and their eruptions were made b: recovered are tholeiitic and transitional basalt. This observation led nearly all the earliest visitors to the Hawaiian Islands. Description Moore and others (1982) to conclude that Loihi Seamount, and of particular note are those of William Ellis (1823), George, Lon perhaps all Hawaiian volcanoes, initially erupt alkalic basalt. Later, Byron (1826), Joseph Goodrich (1826, 1834), and Titus COal I. THE HAWAIIAN·EMPEROR VOLCANIC CHAIN PART I 9 TABLE 1. I.-Hawaiian eruptive producb 100 HAWAIIAN RIDGE Eruptive stage Rock types Eruption Volume rate (percent) Rejuvenated -- alkalic basalt Very low basanite nephe 1ini t e ! nepheline melilitite 0 0 0 ~ 0 N 0 N, e ~ Postshield --- alkalic basalt Low ~ 0 transitional basalt ~ s ~ ankaramite ~ 0 hawaiite > 0 mugearIte . g ~ § -c benmoreite , ,, "~ trachyte I phone lite Shield ------- tholeiitic basalt High 95-98 20 olivine tholeiitic basalt w picritic tholeiitic basalt o icelandite (rare) -c rhyodacite (rare) lalkalic basalt (1) o 2000 4000 Preshield ---- basanite Low alkalic basalt DISTANCE FROM KILAUEA, IN KILOMETERS transitional basalt ltholeiitic basalt (7) FIGURE 1.3.-Age of oceanic crust when overlying volcano formed, as a function lWright and Helz (chapter 23) suggest that the shield stage may of distance from Kilauea, for selected volcanoes in Hawaiian-Emperor Chain. include rare intercalated alkalic basalt and that the preshield stage includes tholeiitic basalt. We suspect that tholeiitic and alkalic Note offsets at fracture zones. Along Hawaiian Ridge both crust and volcanoes basalt occur intercalated during the transitions from preshield to increase in age 10 west so crustal age when volcanoes formed is roughly constant. shield stage and from shield stage to poatshield stage but that during On the other hand, Emperor Seamounts increase in age 10 north but crust the main shield stage only tholeiitic lava is erupted. decreases in age; thus age of crust when seamounts formed decreases from roughly 75 Ma at the bend to less than 40 Ma at Suiko Seamount. milestone because it added detailed descriptions and chemical analyses of rocks from Hawaiian volcanoes other than Kilauea and Mauna Loa.
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